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This is an Open Access document downloaded from ORCA, Cardiff University's institutional repository: http://orca.cf.ac.uk/124701/ This is the author’s version of a work that was submitted to / accepted for publication. Citation for final published version: Dodd, Matthew S., Papineau, Dominic, She, Zhenbing, Fogel, Marilyn L., Nederbragt, Sandra and Pirajno, Franco 2018. Organic remains in late Palaeoproterozoic granular iron formations and implications for the origin of granules. Precambrian Research 310 , pp. 133-152. 10.1016/j.precamres.2018.02.016 file Publishers page: https://doi.org/10.1016/j.precamres.2018.02.016 <https://doi.org/10.1016/j.precamres.2018.02.016> Please note: Changes made as a result of publishing processes such as copy-editing, formatting and page numbers may not be reflected in this version. For the definitive version of this publication, please refer to the published source. You are advised to consult the publisher’s version if you wish to cite this paper. This version is being made available in accordance with publisher policies. See http://orca.cf.ac.uk/policies.html for usage policies. Copyright and moral rights for publications made available in ORCA are retained by the copyright holders. 1 Organic remains in late Palaeoproterozoic granular iron formations 2 and implications for the origin of granules 3 Matthew S Dodda,b, Dominic Papineaua,b, Zhenbing Shec, Marilyn L. Fogeld, Sandra 4 Nederbragte, Franco Pirajnof, 5 aLondon Centre for Nanotechnology, 17-19 Gordon Street, University College London, London, WC1H 0AH, UK. 6 bDepartment of Earth Sciences, University College London, London, WC1E 6BT, UK. 7 cSchool of Earth Sciences & State Key Laboratory of Biogeology and Environmental Biology, China University of Geosciences, Wuhan, 8 China. 9 dDepartment of Earth Sciences, University of California, Riverside 900 University Ave. Riverside, CA 92521, USA 10 eSchool of Earth and Ocean Sciences, Cardiff Univeristy, Cardiff, CF10 3AT, UK. 11 fCentre for Exploration Targeting, The University of Western Australia, 35 Stirling Highway, Crawley, WA 6009 12 Australia 13 14 Keywords: iron formation, Proterozoic, microfossil, carbon isotopes, granules 15 Toward the end of the Palaeoproterozoic era, over 109 billion tonnes of banded (BIF) and 16 granular (GIF) iron formations were deposited on continental platforms. Granules in iron 17 formations are typically sub-spherical structures 0.2 to 10 mm in size, whereas concretions 18 are larger than 10mm. Both types of spheroids are preserved throughout the 19 sedimentological record. Their formation has typically been interpreted to originate from 20 reworked Fe-rich sediments in high-energy, wave-agitated, shallow-marine environments. 21 New evidence from six different late Palaeoproterozoic granular iron formations (GIF), 22 however, suggests that some granules are the result of diagenetic reactions, in addition to 23 other features driven by microbial processes and mechanical movements. Characteristic 24 coarse grain interiors and septarian-type cracks inside granules, akin to those features in 25 decimetre- to meter-size concretions, are interpreted as dessication features from 26 hydrated diagenetic environments where sulphate and/ or ferric iron were reduced while 27 organic matter (OM) was oxidised inside granules. Those granules derived from sulphate 28 reduction preserve diagenetic pyrite rims, whereas those formed via ferric iron reduction 29 preserve diagenetic magnetite along their rims. Other diagenetic minerals including 30 apatite mixed with OM, and various carbonate phases are commonly preserved within 1 31 granules. Combined with systematically 13C-depleted carbonate, these diagenetic mineral 32 assemblages point to the oxidative decay of OM as a major process involved in the 33 formation of granules. Spheroidal equidistant haematite laminations surround some 34 granules and contain apatite associated with carbonate, OM, and ferric-ferrous silicates, 35 and oxides that further suggest these structures were not shaped by wave-action along 36 sediment-water interfaces, but rather by chemical wave fronts and biomineralisation. Our 37 results demonstrate that the formation mechanisms of GIF also involve microbial activity 38 and chemically-oscillating reactions. As such, granules have excellent potential to be 39 considered as promising biosignatures for studying Precambrian biogeochemistry, as well 40 as astrobiology. 41 42 1.0 Introduction 43 Granules are common textures in a variety of chemical sedimentary rocks 44 (Lougheed, 1983; She et al., 2013) and are found from the beginning of the sedimentary 45 rock record through to present day sediments (Pye et al., 1990). Their association with 46 some of the earliest evidence for microbial life on Earth (Schopf and Kudryavtsev, 2012) 47 make them an important sedimentological feature in astrobiological studies. A number of 48 terms have been used to describe granular textures in sedimentary rocks, such as ooid, 49 pisoid, peloid, oncoid, nodule or concretion. The array of terms reflects their variably 50 interpreted origins and the diversity of structures for different spheroidal sedimentary 51 features (Neuendorf et al., 2005). The origin of granules in granular iron formations (GIF) is 52 debated as to whether they reflect sediment reworking (Akin et al., 2013; Simonson, 2003), 53 mineral precipitation (Stefurak et al., 2015) or biological origins (Dahanayake and Krumbein, 2 54 1986; Salama et al., 2013). Herein we adopt the term granule for all spheroidal sedimentary 55 structures 0.2-10mm in size. Larger granules (i.e. >10mm in size) are referred to as 56 concretions. 57 Granular iron formations increased in abundance from ca. 2,000 to 1,500 Myr ago in 58 the aftermath of the Great Oxidation Event (Trendall, 2002), during a period of intense 59 global volcanism (Rasmussen et al., 2012). However GIF have also been recognised in much 60 older deposits, for example in the ca. 2,460 Myr Kuruman-Griquatown IF, South Africa 61 (Beukes and Klein, 1990; Pickard, 2003) and the ca. 2,940 Myr Witwatersrand-Mozaan 62 basin, South Africa (Beukes and Cairncross, 1991; Smith et al., 2017). The occurrence of 63 GIFs, in association with shallow-marine sediments with current-generated structures, has 64 led to the conclusion by some that granules in these rocks represent sediments disrupted by 65 currents and wave action (Akin et al., 2013; Lascelles, 2007; Pufahl and Fralick, 2004; 66 Simonson, 2003), while granules with irregular layering in GIFs have been attributed to 67 stromatolitic growth of microbial colonies (Smith et al., 2017; Walter et al., 1976). Others 68 have proposed that some Precambrian granules may represent a unique style of silica 69 precipitation, whereby stages of silica aggregation of nanospheres, prompted by changes in 70 water chemistry, produced episodic granule formation (Stefurak et al., 2015). Alternatively, 71 the curved, equidistant laminations around granules may be explained by diagenetic growth 72 during oxidation of OM. These processes may be biologically-mediated or abiotic reactions 73 proceeding as chemically-oscillating reactions such as the Belousov-Zhabotinsky (B-Z) 74 reaction (Zaikin and Zhabotinsky, 1970), as was suggested for the formation of rosettes and 75 granules in the Lake Superior area (Papineau et al., 2017). The B-Z oscillating type reactions 76 proceed with solutions containing, for example, malonic acid, sulphate and bromate- 77 bromide. These reactions produce a switch in the oxidation state of ferroin, which is used in 3 78 the reaction to see changes in redox state between periodic oxidised fronts. Their patterns 79 are fractal as they repeat in shape and size proportion at different length scales, and can be 80 described as curved equidistant laminations that propagate outward as chemical waves. In 81 light of this and the potential role of microbial activity in GIFs we describe the characteristics 82 of granules, the microfossils found within, and their mineralogy in six different IFs from 83 around the world during the late Palaeoproterozoic. 84 2.0 Geological setting of the six studied late Palaeoproterozoic GIFs 85 All granular IFs described in this study formed in separate, tectonically active basins, 86 between 2.0 Ga and 1.6 Ga along shallow continental shelves and are stratigraphically 87 associated with major stromatolitic horizons. 88 2.1 Chuanlinggou iron formation 89 The Chuanlinggou IF (also known as Xuanlong-type iron deposit) is part of the 90 Changcheng Group and located in north-western Hebei province, China (Luo et al., 2014). 91 The Chuanlinggou Fm. is 40-90m thick and comprises a lower ore section of granular and 92 stromatolitic ironstones and upper shale member (Fig. 1A-D; 2A; 3A-C). This ore section is 93 composed of siltstones, sandstones and ferruginous sandstones intercalated with beds of 94 iron ore. Each ore bed is typically composed of a lower GIF layer with an upper part 95 dominated by stromatolitic iron formation and at the top of each bed occurs a thin layer of 96 siderite. Ripple marks and mud cracks now filled with chert and carbonate occur in the light 97 green mudstone between iron ore beds suggestive of a shallow-marine to intertidal 98 depositional setting. The formation was deposited in the Yanshan continental rift basin 99 between 1638 ± 14 Ma and 1673 ± 10 Ma based on U-Pb dating of diabase in the 100 Chuanlinggou Fm (Gao et al., 2009) and intrusive granite dykes (Li et al., 2011). This 4 101 continental rift basin has been linked to the initial breakup of the supercontinent Nuna from 102 1.6-1.2 Ga (Kusky and Li, 2003). The samples were collected from Pangjiapu quarry, 103 Zhangjiakou city, Hebei Province (40°37'42.16"N, 115°27'49.29"E). 104 2.2 Biwabik iron formation 105 The Biwabik IF forms part of the Palaeoproterozoic Animikie Group in the Lake 106 Superior region of the USA and Canada. It is one of many separate but coeval IFs deposited 107 in the group. The age of the IF is constrained by U-Pb dating from associated volcanic beds 108 bounding the formations, yielding minimum and maximum ages of 1874±9 Ma (Schneider et 109 al., 2002) and 1878±1.3 Ma (Fralick et al., 2002).

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